Malacological and sedimentological evidence for ‘‘warm ...glacial climate from the Irig loess...

Malacological and sedimentological evidence for ‘‘warm’’glacial climate from the Irig loess sequence, Vojvodina,Serbia

Slobodan B. MarkovićChair of Physical Geography, University of Novi Sad, Trg Dositeja Obradovića 3, 21000 Novi Sad, Serbia([email protected])

Eric A. OchesDepartment of Geology, University of South Florida, 4202 East Fowler Avenue, SCA 528, Tampa, Florida 33620,USA ([email protected])

William D. McCoyDepartment of Geosciences, University of Massachusetts, Amherst, Massachusetts 01003, USA ([email protected])

Manfred FrechenLeibniz Institute for Applied Geosciences (GGA-Institut), Geochronology and Isotope Hydrology, Stilleweg 2,D-30655 Hanover, Germany ([email protected])

Tivadar GaudenyiChair of Physical Geography, University of Novi Sad, Trg Dositeja Obradovića 3, 21000 Novi Sad, Serbia([email protected])

[1] Four loess units and three paleosol layers are preserved in the Irig brickyard, Vojvodina, Serbia. Aminoacid geochronology provides stratigraphic correlations between loess units V-L1 and V-L2 at the Irigsection with loess of glacial cycles B and C, respectively, described from other central European localities.Luminescence dating results for the upper loess layers V-L1L1 and V-L1S1L1 confirm the geologicalinterpretations, although in samples below paleosol V-L1S1S2, the age increase with depth is less than inour proposed age model. Magnetic susceptibility and sedimentological evidence from the Irig loess-paleosol sequence show general similarities with the MIS 6-1 pattern of the SPECMAP oxygen-isotopecurve. Malacogical investigations at the Irig site reveal the continuous presence of the Chondrula tridensand Helicopsis striata faunal assemblages throughout the last glacial and final part of the penultimateglacial loess. The loess snail fauna, which is characterized by the complete absence of cold-resistantspecies, suggests a stable, dry, and relatively warm glacial climate, compared with other central Europeanloess localities. Furthermore, these data suggest that the southern slope of Fruška Gora was a refugium forwarm-loving and xerophilus mollusc taxa during the otherwise unfavorable glacial climates of the LatePleistocene.

Components: 6668 words, 7 figures, 2 tables.

Keywords: Irig; Serbia; loess; molluscs; Late Pleistocene; paleoclimate; paleoenvironment.

Index Terms: 3344 Atmospheric Processes: Paleoclimatology (0473, 4900); 3305 Atmospheric Processes: Climate change

and variability (1616, 1635, 3309, 4215, 4513).

G3G3GeochemistryGeophysicsGeosystemsPublished by AGU and the Geochemical Society

AN ELECTRONIC JOURNAL OF THE EARTH SCIENCES

GeochemistryGeophysics

Geosystems

Article

Volume 8, Number 9

19 September 2007

Q09008, doi:10.1029/2006GC001565

ISSN: 1525-2027

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http://dx.doi.org/10.1029/2006GC001565

Received 21 December 2006; Revised 17 May 2007; Accepted 3 July 2007; Published 19 September 2007.

Marković, S. B., E. A. Oches, W. D. McCoy, M. Frechen, and T. Gaudenyi (2007), Malacological and sedimentological

evidence for ‘‘warm’’ glacial climate from the Irig loess sequence, Vojvodina, Serbia, Geochem. Geophys. Geosyst., 8,

Q09008, doi:10.1029/2006GC001565.

1. Introduction

[2] The processes of formation, transport, deposi-tion, and post-depositional modification of aeoliandust are intimately coupled to changes in regionaland global climate. Present global aeolian dustdeposition is significantly lower than it was duringglacial periods. Intensive glacial-period dust accu-mulation was widespread across the midlatituderegions of the globe. In contrast, during intergla-cials, the climate was warmer and generally wet-ter, which led to enhanced pedogenesis,accompanied by minor dust influx. Numerousclimatic oscillations are marked by alternatingloess and soil units documenting Pleistocene pale-oclimatic and paleoenvironmental evolution. Re-cently, the last glacial-interglacial loess-paleosolrecord has received considerable research attentionbecause of high accumulation rates, widespreadoccurrence, and a well developed chronologicalframework [e.g., Evans and Heller, 2001; Porter,2001; Frechen et al., 2003; Roberts et al., 2003;Prins et al., 2007].

[3] The loess-paleosol sequences of the last gla-cial-interglacial cycle from western, central, andeastern Europe recorded many climatic oscilla-tions and different environments ranging fromtundra-like landscapes to humid interglacial for-ests [e.g., Kukla, 1975, 1977; Kukla and Cilek,1996; Vandenberghe et al., 1998; Vandenbergheand Nugteren, 2001; Rousseau et al., 1998, 2001,2002; Antoine et al., 1999, 2001]. In contrast,climate reconstructions from loess of the Vojvo-dina region in northern Serbia indicate a smallerrange of temperature and precipitation variationsand reduced late Pleistocene malacofaunal diversi-ty through the last interglacial-glacial cycle, com-pared with more northerly sites [e.g., Marković etal., 2004a, 2004b, 2005, 2006, 2007; Gaudenyi etal., 2003].

[4] In this study we investigate the sedimentolog-ical and malacological record of late Pleistoceneclimate and environment from the loess sequenceat Irig, on the south slope of Fruška Gora, inVojvodina, Serbia. Using amino acid racemization

and optically stimulated luminescence dating meth-ods, combined with a detailed reconstruction ofpaleoenvironmental parameters, we present evi-dence for ‘‘warm and dry’’ loess accumulation inthis region of Serbia. This contrasts with paleocli-matic reconstructions from other parts of the loessbelt of Europe, where loess typically formed ina periglacial, or tundra-steppe environment.This study highlights the importance of the Irigloess-paleosol sequence for understanding theenvironmental dynamics recorded in southeasternEuropean loess deposits and how it differs fromother European regions for the time period of thelast 150,000 years.

[5] The Irig loess-paleosol sequence (45�050N lat-itude; 19�520E longitude) is exposed in a brickyardsituated on the east bank of Jelence Stream in thecentral part of the south loess slope of Fruška Gora(Figures 1 and 2). An approximately 80 km long,15 km wide, E-W trending range of mountains,reaching only about 540 m elevation, Fruška Gorais flanked by a thin mantle of loess, from theDanube and Sava alluvial plains up to an elevationof approximately 400 m. Four loess layers andthree fossil soils are exposed in the approximately8 m thick sediment sequence at Irig.

[6] Present-day climate in the region is continental,with air masses from northern and western Europefunneling into the southern Carpathian (Pannonian)Basin. The Dinaric Alps to the west block mostMediterranean influence, although warm, moistAdriatic air reaches the southern part of Serbia.The investigated region is characterized by meanannual temperatures of 11.1�C, with summersaveraging about 21�C and winters averaging only0.6�C. Mean annual precipitation, which is domi-nated by summer rainfall, is about 610 mm.

2. Material and Methods

[7] The investigations of the loess-paleosolsequences at the Irig quarry began in 2001. Bulksediment samples were collected at 5-cm intervalsfor granulometric analysis, and at 25-cm intervalsfor malacological studies. Dry and moist colors of

GeochemistryGeophysicsGeosystems G3G3 markoviĆ et al.: irig loess sequence, vojvodina, serbia 10.1029/2006GC001565

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the loess and paleosol were described using Mun-sell Soil Color Charts. Grain size (GS) fractions(200 mm) were measured bysieving and pipeting, following procedures noted inMarković et al. [2004a], and carbonate content wasanalyzed gas volumetrically. Magnetic susceptibil-ity (MS) variations were measured in the fieldusing a portable Bartington susceptibility meter.

Measurements were recorded at 5-cm intervals; tenindependent readings were averaged for each level.

[8] Fifteen-kilogram bulk sediment samples formalacological investigations were sieved through0.7 mm mesh. After fossil gastropod shells wereidentified, paleoenvironmental classification wasdone by comparison with the interpretations ofLožek [1964], but also extended with some local

Figure 1. Geographic position of the Irig brickyard exposure and other relevant sites in the Vojvoida loess region.

Figure 2. Topographic map of the area surrounding the Irig brick mine. Position of the investigated exposure isindicated by arrow.

GeochemistryGeophysicsGeosystems G3G3 markoviĆ et al.: irig loess sequence, vojvodina, serbia 10.1029/2006GC001565markoviĆ et al.: irig loess sequence, vojvodina, serbia 10.1029/2006GC001565

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variants, as defined by Krolopp and Sümegi [1995]and Sümegi and Krolopp [2002]. July paleotem-peratures were estimated using the malaco-paleo-thermometer method of Sümegi [1989, 1996]and Herelendi et al. [1992]. This method is basedon modern geographic and climatic ranges of11 dominant gastropod species from a compositemalacofauna [Sümegi, 1996]. For selected gastro-pod species, optimal climatic conditions can bedetermined along the minimum and maximumtemperature values of tolerance (activity range ofgastropods) with respect to actual climatologicaldata.

[9] Gastropod shells were collected from threelevels within V-L1 (last glacial loess) and theuppermost part of V-L2 (penultimate glacial loess)for amino acid racemization analysis in order tocorrelate the stratigraphy independently with pre-sumed synchronous loess-paleosol units elsewherein Europe. Details of the sample preparation andanalytical procedures are presented by Oches andMcCoy [2001].

[10] Infrared optically stimulated luminescence(IRSL) measurements were carried out on 4 loesssamples, three of which were taken from abovethe strongly developed paleosol V-S1 and onefrom below the paleosol. IRSL samples werecollected in light-proof containers at depths of1.70 m, 3.40 m, 5.30 m and 7.50 m. Polymineralfine-grained material (4–11 mm) was prepared forthe determination of equivalent dose, as described

by Frechen et al. [1996]. The samples were betairradiated by a 90Sr beta source in at least seven dosesteps with five discs each and a maximum radiationdose of 750Gray (Gy). All discs were stored at roomtemperature for at least four weeks after irradiation.The irradiated samples were preheated for 1 minuteat 230�C before infrared stimulation. Equivalentdose values were determined using IRSL. A SchottBG39/Corning 7–59 filter combination was placedbetween photomultiplier and aliquots for IRSLmeasurements. A 10 s IR exposure was applied toobtain their IRSL signals. The equivalent dose wasobtained by integrating the 1–10 s region of theIRSL decay curves using an exponential fit. Alphaefficiency was estimated to a mean value of 0.08 ±0.02 for all samples [cf. Lang et al., 2003]. Doserates for all samples were calculated from potassi-um, uranium and thorium contents, as measured bygamma spectrometry in the laboratory, assumingradioactive equilibrium for the decay chains. Cos-mic dose rate was corrected for the altitude andsediment thickness, as described by Aitken [1985]and Prescott and Hutton [1994]. The natural mois-ture content of the sediment was estimated to 15 ±5% for all samples.

3. Results

3.1. Lithostratigraphy and Pedostratigraphy

[11] The stratigraphic framework of loess in theVojvodina region is relatively simple. Eolian dust

Figure 3. Stratigraphy of the Irig brickyard exposure. Positions of samples for amino acid analysis are indicated byarrows. Total hydrolysate (HYD) alloisoleucine/isoleucine (A/I) values are shown for the gastropod genera Pupillaand Vallonia. Number in parentheses indicates the number of individual shells separately prepared and analyzed.Legend: 1, loess; 2, chernozem-like A horizon; 3, chernozem A horizon; 4, root infiltrations; 5, carbonateconcretions; 6, crotovinas.


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accumulated semi-continuously on a nearly hori-zontal platform of the Pannonian plain, which is amorphologically similar setting to the Chineseloess plateau [e.g., Liu, 1985; Kukla, 1987; Kuklaand An, 1989]. Following the same criteria pre-sented in more recent studies [Marković et al.,2004b, 2005, 2006, 2007], we describe and strati-graphically characterize three paleosol and fourloess layers at the Irig quarry (Figures 2 and 3 andTable 1). We use the prefix ‘‘V’’ to refer to thestandard Pleistocene loess-paleosol stratigraphy inthe Vojvodina region. Loess unit V-L2 is about100 cm thick, correlates to the penultimate glacialperiod, and is exposed in the lower part of profileas a result of the brickyard excavation. V-L2 loessis covered by the strongly developed interglacial-early glacial soil complex V-S1, which has athickness of 245 cm. The last glacial loess unitV-L1 and the Holocene soil V-S0 have thicknessesof 405 cm and 45 cm, respectively. Major changesin color, sedimentology and magnetic propertiesoccur at the contacts of loess horizon V-L2, pale-osol V-S1, loess layer V-L1, and recent soil V-S0.These lithological changes correlate very likelyto marine oxygen-isotope stage (MIS) 6/5, 5/4,and 2/1 transitions. Table 1 shows the detailedmorphological description of the loess-paleosolsequence at the Irig section.

3.2. Geochronology

[12] Stratigraphic correlations with the marineoxygen-isotope record are supported by interpre-tations based on relative dating of V-L1 and V-L2loess by amino acid racemization (AAR) andnumerical age estimates on V-L1 loess frominfrared optically stimulated luminescence (IRSL)methods.

[13] Amino acid racemization geochronology,using fossil terrestrial gastropod shells, hasbeen successfully applied to mollusks from loess-paleosol sequences in different regions of the world[Oches and McCoy, 2001] resulting in a morereliable correlation and paleoclimatic interpretationthan previously. Shells of the gastropod generaPupilla, Vallonia, and Helicopsis were found indifferent levels at the Irig section. They wereanalyzed for D- and L-stereoisomers of severalamino acids by reverse-phase liquid chromatogra-phy following the methods described by Kaufmanand Manley [1998]. This study focuses on theratios of diastereoisomers D-alloisoleucine andL-isoleucine (A/I) in Pupilla and Vallonia shells.Data from other amino acids, including D/L-aspartic acid, glutamic acid, valine, and phenylal-anine, are in agreement with A/I data. The resultsof total hydrolysate (HYD) A/I measurements onrepresentative samples are shown in Figure 3.Pupilla and Vallonia shells yielded reproducible

Table 1. Morphological Description of the Loess-Paleosol Sequence at the Irig Brickyard Exposure

Unit/Subunit

Thickness,cm Depth, cm Description

V-S0 45 0–45 Modern soil is a chernozem on the loess plateau. The lower Ck horizoncontains many CaCO3 nodules of 1–3 cm diameter and numerouscrotovinas and root channels filled with humic material.A transitional AC horizon (10YR 5/1–3/3) is 10 cm thick andconsists of silt loam with fine blocky structure and abundant pseudomycelia.The Ah horizon (10YR 6/3–4/4) is a 20 cm thick silt loam with granularstructure and some carbonate pseudomycelia.

V-L1 405 46–450 Porous pale yellow loess (5YR 7/3, 5/4).V-L1L1 135 46–180 Very porous, pale yellow loess (10YR 7/4–5/3) with many humic infiltrations

and soft spherical carbonate concretions (ø �5 cm), intensively bioturbated.V-L1 S1 125 181–235 V-L1S1S1: the upper 10YR 6/4 = 2–4/2) mollic Chernozem-like A horizon with

weak granular structure.236–250 V-L1S1L1: thin loess layer (10YR 6/3 4/2) with carbonate concretions (ø 1–2 cm).251–305 V-L1S1S2: the lower 10 YR 6/3–4/2 mollic Chernozem-like A horizon with

carbonate pseudomycelia.V-L1L2 145 306–450 Porous pale yellow loess (5YR 7/3, 5/4).V-S1 245 451–695 Strong developed chernozem-pedocomplex: the lower Ah horizon has weak platy

structure (10YR 5/2–3); the upper mollic A horizon with brighter color(10YR 6/2–4) and many carbonate pseudomycelia.

V-L2 �100? 696-? Porous yellow (5YR 7/3, 5/4) loess with many humus infiltrations and carbonateconcretions (ø 1–3 cm).


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A/I measurements from V-L2 and V-L1 loess unitsand offer the most direct aminostratigraphic com-parison with data from synchronous loess units atAustrian, Czech, Slovakian, Hungarian and Ger-man sites [Zöller et al., 1994; Oches and McCoy,1995a, 1995b, 2001; Oches et al., 2000; Novothnyet al., 2007] (Figure 4). Amino acids in Pupilla andVallonia shells racemize at comparable rates, andthe A/I ratio can be directly compared between thetwo taxa [Oches and McCoy, 1995a]. HYD A/Ivalues measured in Pupilla and Vallonia from V-L2loess (0.18 ± 0.02, n = 3) are twice as high as thosefrom V-L1 loess (0.08 ± 0.01, n = 4), which istypical for the differences in ratio observed insamples bracketing the last interglacial paleosol.Furthermore, we determined comparable, thoughslightly lower, values in shells from loess of thepenultimate and last glacial loess investigated else-where in central Europe, as shown in Figure 4.

[14] Present-day mean annual temperatures arehigher in southern Hungary and Serbia than inthe more northern regions. A higher effectivediagenetic temperature can explain the more rapidrate of racemization, and therefore higher A/I

values, in samples from the Vojvodina loess, com-pared with synchronous loess units from othercentral European sites [Marković et al., 2004b,2005, 2006, 2007; Oches et al., 2004]. The HYDA/I values measured in Pupilla and Vallonia showthat the method can clearly distinguish betweenloess of the two last glacial cycles. These datasupport the correlation of V-L2 and V-L1 loesswith MIS 6 and MIS 4-2, respectively. Note,however, that these amino acid data cannot distin-guish between V-L1L1 and V-L1L2 at Irig.

[15] Luminescence dating (Table 2) provides ameans for establishing numerical ages for thelast glacial loess, although age underestimation isapparent for the sample taken from the V-L2loess. Similar observations were made for samplesfrom other European loess regions [Wintle andPackman, 1988; Frechen, 1992; Frechen et al.,1997]. Uranium, thorium and potassium contentrange from 3.20–3.27 ppm, 10.93–12.99 ppm, andfrom 1.50–1.96%, respectively, resulting in a cal-culated dose rate between 3.90 and 4.40 Gy/ka.The mean dose rate is 4.09 Gy/ka (n = 4), which isin the range of central European loess [cf. Frechenet al., 2001]. The IRSL equivalent dose valuesincrease with depth from 72.5–368.3 Gy. IRSL ageestimates are 18.6 ± 1.6 ka for the uppermost loesslayer V-L1L1, 42.3 ± 3.3 ka for loess associatedwith the weak interstadial paleosol, 34.5 ± 2.8 kafor the lower unit of the V-L1 loess horizon, and83.6 ± 6.4 ka for the uppermost part of thepenultimate glacial loess V-L2 (Table 2). An un-explained stratigraphic inversion is apparent inIRSL ages between samples 3 (V-L1S1L1) and 2(V-L1L2). The lowermost age estimate is verylikely significantly underestimated by >50%.Results for samples from penultimate glacial loessin Hungary [Wintle and Packman, 1988; Frechenet al., 1997], Germany [Frechen, 1999] andKazakhstan [Machalett et al., 2006] gave similarage underestimations. Anomalous fading could be

Figure 4. Aminostratigraphy of the Irig brickyardsection compared with other representative centralEuropean localities for glacial cycles C and B,corresponding to marine oxygen-isotope stages 7–6and 5–2, respectively, for the genus Pupilla. H,Hungary; CZ, Czech Republic; SK, Slovakia; A,Austria; D, Germany.

Table 2. Luminescence Data and Ages, Including Depth Below Surface, Uranium, Thorium, and PotassiumContent, Cosmic Dose Rate, Total Dose Rate, Paleodose, and IRSL Age Estimatesa

Sample

LUMLab

NumberDepth,m

Strat.Unit

U,ppm

Th,ppm K, %

Cosmic,mGy/a

Dose Rate,Gy/ka

Paleodose,Gy

Age,ka

4 400 1.70 V-L1L1 3.27 ± 0.06 10.93 ± 0.12 1.50 ± 0.03 190 ± 10 3.90 ± 0.30 72.5 ± 3.1 18.6 ± 1.63 401 3.40 V-L1S1L1 3.20 ± 0.05 11.98 ± 0.10 1.59 ± 0.02 168 ± 8 4.04 ± 0.31 171.1 ± 3.4 42.3 ± 3.32 399 5.30 V-L1L2 3.36 ± 0.07 11.26 ± 0.12 1.64 ± 0.03 149 ± 7 4.05 ± 0.31 139.4 ± 4.0 34.5 ± 2.81 398 7.50 V-L2 3.22 ± 0.05 12.99 ± 0.10 1.96 ± 0.03 129 ± 7 4.40 ± 0.34 368.3 ± 3.9 83.6 ± 6.4

aU, uranium; Th, thorium; K, potassium. Alpha efficiency is 0.07 ± 0.01. Moisture (estimated) is 15 ± 5%.


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the reason for these age underestimations, althoughshort-time fading tests have not indicated a signif-icant fading rate.

3.3. Sedimentological and MagneticInvestigations

[16] Sedimentological data parallel lithologic var-iations within the profile, which reflect changes inpast climatic and environmental conditions. Mag-netic susceptibility (MS), grain-size (GS), andcarbonate content measurements reveal patternsthat can be correlated with the SPECMAP marineoxygen-isotope record of the last 150,000 years[Martinson et al., 1987]. Variations of MS arerelated to soil forming processes and reflect differ-ences in composition, concentration, and particlesize of magnetic minerals between interglacial andglacial-age sediments [e.g., Evans and Heller,2001]. At Irig MS values measured in soils V-S1(average 61.1 SI units) and V-S0 (average 40.0 SIunits) are higher than those measured in loess unitsV-L1 (average 21.8 SI units) and V-L2 (average18.7 SI units) (Figure 5). Interstadial paleosols V-L1S1S2 and V-L1S1S1 have relatively low MSvalues, compared with interglacial soils V-S1 andV-S0, and are only slightly higher than valuesmeasured in loess. This type of MS pattern reflectsmagnetic enhancement via pedogenesis and issimilar to that observed in Chinese and CentralAsian loess deposits [e.g., Heller and Liu, 1986;Maher and Thompson, 1999].

[17] Variations in GS distribution also coincidewell with the pedostratigraphy of the Irig sequence

(Figure 5). Variability in clay content (200 mm) is rather invariant, except for asignificant enhancement in the upper part of thepenultimate glacial loess, V-L2, and minorincreases near the base of paleosol S1 and withinV-L1L2 (Figure 5).

[18] At the Irig section, the carbonate contentthroughout the profile ranges from 0 to 16%,independent of (paleo)soil formation (Figure 5).In contrast to other investigated loess profiles in theVojvodina region [Marković et al., 2004a, 2004b,2005], the Irig section is characterized by a lowerabundance and smaller sizes of carbonate concre-tions. Carbonate content variations in the Irigloess-paleosol sequence show a different pattern,compared with carbonate records from other loesssequences in the Vojvodina region. In general,loess from other profiles in Vojvodina have a highcarbonate content, but the soils are mostly decal-cified [Marković et al., 2004a, 2004b, 2005].

3.4. Malacological Investigation

[19] In our malacological analysis, shells of 735individuals representing 14 species (12 genera)

Figure 5. Depth plots of magnetic susceptibility, clay content (200 mm, carbonate content, and inferred July paleotemperatures based on the malaco-thermometer method, andIRSL ages at the Irig exposure, compared with the SPECMAP paleoclimate record [Martinson et al., 1987].


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were collected from 32 samples. Results are sum-marized in Figure 6. The fossil gastropod assem-blage from the upper part of the V-L2 horizon ischaracterized by a higher abundance of shells persample than those from the last glacial loess V-L1.The final stage of the penultimate glacial interval ischaracterized by the presence of species such asVallonia costata and Clausilia dubia indicatingrelatively cold and somewhat semi-arid climate[Ložek, 1964; Sümegi and Krolopp, 2002]. Noland-snail shells were found in the lower parts ofpaleosol S1 due to poor preservation and leachingof primary carbonates in the soil. The dominanceof temperate thermophilous and aridity-tolerantsnails such as Chondrula tridens, Granaria fru-mentum, Helicopsis striata, and Pupilla triplicatain loess V-L1 indicates open vegetation and amostly dry environment related to steppe-likegrassland [Ložek, 1964]. Generally, our identifiedland snail record represents equivalents of theChondrula tridens fauna, which is a typical com-munity associated with interstadial chernozemsoils, and the Helicopsis striata fauna, which is acharacteristic assemblage of the ‘‘warm’’ loessenvironment in central Europe, as defined by Ložek[1964, 2001]. Overall, the terrestrial malacological

assemblages reflect a dominantly grassland envi-ronment at Irig.

4. Discussion

[20] Paleoclimatic and paleoenvironmental recon-structions derived from the loess-paleosol sequenceat the Irig quarry show similarities with previouslyinvestigated Late Pleistocene loess sites in theVojvodina region [Marković et al., 2004a, 2004b,2005, 2006]. The uppermost part of the penultimateglacial loess V-L2 and three last glacial loess layersV-L1L2, V-L1S1L1 and V-L1L1 accumulated dur-ing dry and temperate stadial intervals. Duringinterstadial and interglacial periods, the climatewas warmer and generally wetter, which led toenhanced pedogenesis. The interglacial soils S1and S0 tend to be strongly developed and havesignificant magnetic susceptibility enhancement.In contrast, interstadial paleosols V-L1S1S2 andV-L1S1S1 are weakly expressed and have MSvalues only slightly higher than loess, althoughthey have similar grain-size and carbonate valuesas V-S1 and V-S0. Paleoclimate proxies deter-mined from the loess-paleosol sequence at Irigconform with the general trends in the SPECMAP

Figure 6. Relative abundance diagram of the identified mollusc species in the Irig brickyard loess exposure. Thespecies (as % of total) are clustered in ecological groups based on temperature sensitivity, as defined by Ložek [1964],Krolopp and Sümegi [1995], and Sümegi and Krolopp [2002]: (1) mesophilous and (2) thermophilous.


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[Martinson et al., 1987] model of global paleocli-matic evolution (Figure 5). However, sedimentaryproxies from the MIS-3 correlative paleosols at Irig(V-L1S1S1 and V-L1S1S2) suggest that conditionswere more similar to the last interglacial period alongthe southern slope of Fruška Gora than indicated bythe globally integrated SPECMAP record.

[21] The glacial landscape and paleoenvironment,as recorded in the Irig loess profile, is characterizedby the continuous presence of Chondrula tridensand Helicopsis striata faunas throughout the se-quence, which are typical communities of intersta-dial periods in other parts of central Europe, asdefined by Ložek [1964, 2001]. The most importantcharacteristic of the last glacial and late penulti-mate glacial land-snail assemblages is the absoluteabsence of cryophilous elements and cold resistantspecies at the Irig section, which are typical in full-glacial loess deposits elsewhere in Europe. Con-tinuous semi-arid conditions may have reduced theenvironmental amplitude between the warm anddry interglacial steppe and the ‘‘warm’’ glacialgrassland landscape.

[22] Mean July paleotemperatures at Irig are cal-culated on the basis of the malaco-thermometermethod of Sümegi [1989, 1996] and Herelendi etal. [1992]. The highest (21�C) and lowest (17�C)malacologically determined July paleotemperaturesoccurred during the accumulation of the lower partof loess horizon V-L1L1. Reconstructed paleotem-peratures suggest large temperature changesaround the last glacial maximum (Figure 6). In

the upper part of loess V-L1L1, the malacofaunaindicate stable maximum summer temperaturesbetween about 18�–19�C. On the basis of snailassemblages from pedocomplex V-L1S1 and loesslayers V-L1L2 and V-L2, reconstructed July pale-otemperatures ranged from about 17�–20�C duringthose periods of loess accumulation and interstadialsoil formation. Generally, summer conditions dur-ing the warmer phases of the last glacial period andfinal part of the penultimate glacial interval at Irigwere similar to present (21.5�C). Paleotemperaturereconstructions show somewhat higher values forthe late pleniglacial loess at Irig than in Hungarianloess sections [Krolopp and Sümegi, 1995; Sümegiand Krolopp, 2002]. Furthermore, the absence ofcryogenic features in loess at Irig and elsewhere inVojvodina suggests warmer winters than indicatedfor central European sites to the north and west.

[23] Previous investigations of Ložek [1964] andKukla [1975, 1977] indicate that the Europeanloess belt formed under cold and dry continentalclimate. During the stadial periods, two main coldassemblages were dominant, i.e., the Pupilla andthe Columella communities, essentially correlatingto loess-steppe and tundra-like environments, re-spectively. Rousseau [2001] compared the generalclimate evolution during the last pleniglacial in theEuropean loess belt with the present climate of thecold temperate higher latitudes. However, thoseinterpretations are related only to central, western,and eastern European loess regions and have notbeen extended into the southeastern Europeanregion.

Figure 7. Distribution of the loess sediment across Europe with reconstruction of the continental ice caps during thelast glacial maximum (modified from Moine et al. [2002] and Rousseau [2001]) and the permafrost zone[Vandenberghe et al., 2004]. Legend: 1, loess; 2, ice caps; 3, dry continental shelf; 4, boundary of permafrost zonesouth of the Alps; 5, sites with ‘‘warm’’ glacial climate record.


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[24] Figure 7 shows the distribution of loess depos-its over Europe and the reconstruction of thecontinental ice caps (modified from Moine et al.[2002] and Rousseau [2001]) and the extension ofthe permafrost zone [Vandenberghe et al., 2004]during the last glacial maximum. In contrast to‘‘classical’’ European periglacial loess provinces,the loess of the Carpathian Basin was depositedbeyond the periglacial zone. Late pleniglacial cli-matic and environmental reconstructions provideevidence for higher mean July paleotemperaturesand decreasing humidity from the northern tosouthern parts of the Carpathian Basin during thelate Pleistocene [Krolopp and Sümegi, 1995;Sümegi and Krolopp, 2002]. The Vojvodina regionis presently the warmest and driest part of theCarpathian Basin, and a similar climatic gradientmost likely existed during the late pleniglacialperiod. The absence of cryogenic features and snailassemblages having only few cold-resistant speciesgive strong evidence that the last glacial loessdeposits in the Vojvodina region accumulatedmainly under dry and relatively warm conditionsduring the glacial periods [Marković et al., 2007].Recent studies of the Ruma [Marković et al., 2006]and Požarevac [Jovanović et al., 2006] loess-paleosolsequences suggest similar results for paleoclimaticand paleoenvironmental reconstructions andstrongly indicate that the southeastern margin ofthe Carpathian Basin was very likely situated at thenorthern extent of a southeastern European‘‘warm’’ glacial province.

[25] This study raises questions about the impor-tance of local environmental conditions for loessdeposition. The most important criteria for classi-fying loess deposits are the global climatic con-ditions under which they accumulated. However,deflation and aeolian dust deposition are dependentmore on regional climatic characteristics than onlocal climatic and environmental conditions [e.g.,Wright, 2001; Smalley et al., 2006], includingtemperature, moisture and wind regime underwhich particle generation, entrainment, transportand deposition occurred. The loess of the Irigsection can be classified according to local envi-ronmental conditions as the ‘‘dry warm’’ variety ofthe ‘‘glacial’’ loess deposition model based ongeneral climatic predispositions. In general, loessat the Irig site accumulated and formed whenglobal climate was in a glacial mode. However,reconstruction of local climatic conditions duringthe period of loess deposition indicate significantlywarmer and drier glacial summers and warmerwinters than in other well investigated localities

within the European loess belt [e.g., Kukla, 1975,1977; Vandenberghe et al., 1998; Rousseau et al.,1998, 2001, 2002; Antoine et al., 1999, 2001].

5. Conclusions

[26] Investigations of the loess-paleosol sequenceat Irig have established the importance of this siteas a record of late Pleistocene paleoclimate andpaleoenvironment in Serbia. The Irig section, as theone of the most extensively investigated Serbianexposures, provides an opportunity to reconstructlocal and regional environmental processes andconditions during the late Pleistocene.

[27] Sedimentological, pedological, magnetic, andpaleontological evidence recorded in the Irig loess-paleosol sequence suggest periods of warmer anddrier environmental conditions in this region thanin other parts of the Pannonian (Carpathian) basinduring the last �150,000 years. Identified malaco-fauna reveal important paleoclimatic and paleoen-vironmental interpretations. The southern slope ofthe Fruška Gora was a biogeographical ‘‘island’’during the last glacial period, where a temperategrassland with dry-tolerant and warm-loving faunalelements remained, even in the coldest phases oflate Pleistocene glacial episodes.

Acknowledgments

[28] We thank Mladjen Jovanović and Stevan Savić for theirhelp during the fieldwork and laboratory measurements. We

also wish to thank the Irig Brick factory for allowing the team

to work in the quarry. We are grateful to Jef Vandenberghe,

Ulrich Hambach, and Maarten Prins for helpful, substantive

reviews of this manuscript. This research was supported by

Project 146019 of the Serbian Ministry of Science and Envi-

ronmental Protection and U.S. National Science Foundation

grants ATM-0081754 to Oches and ATM-0081115 to McCoy.

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